Late Devonian Conodont Fauna of the Gümüflali Formation, the Eastern Taurides, Turkey
fiENOL ÇAPKINO⁄LU & ‹SMET GED‹K
Karadeniz Teknik Üniversitesi, Jeoloji Mühendisli¤i Bölümü, TR-61080 Trabzon, TURKEY (e-mail: [email protected])
Abstract: The Late Devonian Gümüflali formation of the eastern Taurides is a terrigenous-carbonate rock sequence about 600 m thick, consisting mainly of quartz sandstone, quartz siltstone, shale, and carbonate rocks.
Palaeontologic and sedimentologic data mainly indicate a shallow subtidal depositional environment. This sequence generally represents the shallow-water polygnathid-icriodid biofacies, and contains conodont faunas that range from the Upper falsiovalis Zone into the Upper praesulcata Zone. However, they do not correlate well to the Late Devonian standard conodont zonation because of the lack of zonally diagnostic species and the irregular vertical distributions of the present taxa. Herein, 54 taxa belonging to nine genera are described and illustrated from the studied section. Icriodus adanaensis, Icriodus fekeensis, and Polygnathus antecompressus are the newly described species.
Key Words: Late Devonian, conodont, Gümüflali formation, eastern Taurides, Turkey.
Gümüflali Formasyonu’nun (Do¤u Toroslar, Türkiye) Geç Devoniyen Konodont Faunas›
Özet: Do¤u Toroslar boyunca yayg›n yüzeylemeleri olan Geç Devoniyen yafll› Gümüflali formasyonu, yaklafl›k 600 metre kal›nl›¤a ulaflan bir k›r›nt›l›-karbonat kaya dizisidir. Litolojisini bafll›ca kuvars kumtafl›, kuvars miltafl›, fleyl ve karbonat kayalar›n›n oluflturdu¤u bu birimin paleontolojik ve sedimantolojik özellikleri, çökelmenin bafll›ca s›¤, gel- git alt› ortamda geliflti¤ine iflaret eder. Konodont faunas› genellikle k›y›-yak›n› polygnathid-icriodid biyofasiyesini temsil eder, ve Üst falsiovalis Zonu’ndan Üst praesulcata Zonu içine kadar uzanan bir aral›¤› temsil eder. Bununla beraber, zon belirleyici taksonlar›n yoklu¤u ve mevcut taksonlar›n düzensiz dikey da¤›l›m›ndan dolay›, Geç Devoniyen standard konodont zonlamas› ile tam bir korelasyon sa¤lanamam›flt›r. ‹ncelenen stratigrafik kesitteki kireçtafl› katmanlar›ndan al›nan 107 örnekten, 9 cinse ait toplam 54 tür ve alttür tan›mlanm›flt›r. Tan›mlanan taksonlardan 3 tanesi (Icriodus adanaensis n.sp., Icriodus fekeensis n.sp. ve Polygnathus antecompressus n.sp.) yeni türdür.
Anahtar Sözcükler: Geç Devoniyen, Konodont, Gümüflali formasyonu, Do¤u Toroslar, Türkiye.
Introduction
Conodont biostratigraphy is one of the most important tools in the correlation of Palaeozoic and Triassic rocks on local, regional, and global scales. In spite of the presence of rocks of this age in Turkey, the studies of their conodont biostratigrahy are few. However, some papers have previously been published on conodonts of Turkey (e.g., Abdüsselâmo¤lu 1963; Gedik 1975, 1977; Önder 1982; Çapk›no¤lu 1991, 1997; Kozur 1997). This paper describes conodont faunas obtained from 107 samples of a single stratigraphic section of the Upper Devonian Gümüflali Formation of the eastern Taurides, and correlates this fauna to the global standard Late Devonian conodont zones (Ziegler & Sandberg 1990). The studied section is located in the village of Çürükler, about 9 km
northeast of the town of Feke, Adana (Turkey), on the
1/25.000 Kozan M35-b2 topographic map, and crops
out along the valley of Göbelli Creek flowing through the
village of Çürükler (Figure 1). The section was measured
using a Jacob’s staff. Its lower 32.50 meters were
sampled along the road on the southwestern side of
Göbelli Creek and the rest along a path on the
northeastern side. Through most of the section, the beds
strike N10-20ºE and dip 60-70ºNW. A total of 170
samples were collected, but only 107 samples yielded
conodont faunas. The samples were processed using
standard acidizing techniques with 10 percent formic
acid. Residues were washed through nested sieves of 63,
100 and 850 microns, but conodonts were only picked
from the residue on the 100-micron sieve.
Lithostratigraphy
The Devonian sequence of the eastern Taurides has been divided into three formation in the previous works: the Lower Devonian Ay›tepesi formation (limestone-shale- sandstone), the Middle Devonian fiafaktepe formation (dolomitic limestone), and the Upper Devonian Gümüflali formation (sandstone-shale-limestone) (Özgül et al.
1973; Metin et al. 1983). The Gümüflali Formation, on which this study is based, has been named for an approximately 600-m-thick terrigenous-carbonate rock sequence overlying the fiafaktepe Formation (Figure 2).
In the study area, it has a faulted contact at its base, and the top is lithologically gradational into the overlying Lower Carboniferous Ziyarettepe Formation. The lithologic sequence consists generally of thin-medium bedded, light grey quartz-sandstone and quartz-siltstone, dark grey marl and laminated shale and limestones, and contains a rich macrofauna consisting mainly of brachiopods, bryozoans and solitary or massive corals
(Figure 2). Corals are abundant in the limestones, and brachiopods and bryozoans in both limestones and other lithologies. The basal portion of the formation is made up of dark grey limestones interbedded with shale or marly shale. The middle part consists of an alternation of limestone and shale with quartz sandstone and siltstone interbeds. The upper 85 meters is dominated by dark grey, silty-sandy, spiculitic limestones.
The carbonate rocks range from mudstone to boundstone. Many samples have packstone and grainstone texture (Figure 2). Skeletal grains and Girvanella-oncoids are the abundant types. Pellets and intraclasts are scarce. Brachiopods (shells and spines), echinoderms (crinoids, echinoids), bryozoans, cyanophycean algae (generally Girvanella sp.), corals and ostracods (Cryptophyllus sp. and others) are the most abundant skeletal particles. Non-carbonate components are generally represented by detrital quartz that locally reaches 30 volume % in some samples. Dolomitization, micritization, silicification, pyritization, and limonite and hematite impregnation were the most widespred diagenetic events. Geopetal structures, sheltering effects and stylolitic structures are the most widespread sedimentologic structures. Abundant bioturbation fabrics are indicated by the arrangement of bioclasts in a circular pattern and by the different packing of particles. Borings are especially abundant in brachiopod shells. Fossil content and sedimentologic characteristics of the Gümüflali Formation indicate a shallow subtidal depositional environment (Çapk›no¤lu 1990, 1991).
Biostratigraphy
The Gümüflali Formation is dominated by conodont species of the polygnathid-icriodid biofacies, together with a few species of the palmatolepid-polygnathid biofacies. Conodonts are generally not abundant, and many parts of the section yielded few or no specimens.
Because of the influence of biofacies, the scarcity or absence of zonally diagnostic taxa and the irregular vertical distributions of many taxa, the standard Late Devonian conodont zones (Ziegler 1962; Ziegler &
Sandberg 1984, 1990) are not readily applicable to the Gümüflali Formation. However, some of them have been described.
The lowest sample (Table 1, sample ÇR2) of the studied stratigraphic section is of Frasnian age, no older
Fekeda¤›
FEKE
C›v›kl›
ÇR170 ÇR27 ÇR1 Göbelli
Creek Adana
BLACK SEA
MEDITERRANEAN SEA
Göksu River
NN
NN TURKEY Feke
2 km 40 km
K›z›lyer Aksu
River Çürükler
AEGEAN SEA
Figure 1. Location map for the studied stratigraphic section.
ÇR140 ÇR150 ÇR160 ÇR170
ÇR130
S
S
Rc H
H
H
Rc
P
P
Rc
M Rc Rc
Rc
F1: Mudstone
F2: Bioclastic wacke-/packstone F3: Coral bafflestone
F4: Coral-bioclastic wackestone F5: Gastropod packstone
F6: Oncoid-bioclastic pack-/grainstone F7: Bioclastic pack-/grainstone F8: Brachiopod pack-/grainstone F9: Brachiopod-echinoderm pack-/grainstone
F10: Brachiopod-echinoderm-bryozoan pack-/grainstone
F11: Ostracod grainstone F12: Dasycladacean algal-bioclastic packstone
F13: Stromatoporoidal-bioclastic packstone
F14: Pelletoidal-bioclastic grainstone F15: Mudstone bearing Umbellina sp.
and pelletoidal-intraclastic grainstone with Umbellina sp.
F16: Spiculitic wacke-/packstone ...
...
...
...
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...
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...
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...
f
f
f ÇR20
ÇR30 ÇR40 ÇR50 ÇR60 ÇR70 ÇR80 ÇR90 ÇR100 ÇR110 ÇR120
m m m m
m m
m m
m m m
m m
m
m m m m m
m m m
m
m m m m
m m m m m
ÇR1
M R
M
H P Rc
M Rc
M
M P M Rc
M Rc
P M
P H M Rc M M Rc
Rc
S
M
ÇR10 P HH
S M P Rc RcM Rc
...
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COVERED COVERED COVERED COVERED COVERED
†
20 m 10 0 SCALE
EXPLANATION
F9 F10 F11 F12 F13 F14 F15 F16 F1
F2 F3 F4 F5 F6 F7 F8 m
Limestone
Shale and marl
Siltstone
Sandstone ...
...
H Hematite impregnation
M Micritization Rc Syntaxial rim cement
Laminated structure Stylolite
Boring Burrowing Sheltering effect Geopetal structure Dolomitization P Pyritization S Silicification
Figure 2. Lithologic development of the studied stratigraphic section and the sample locations.
than the upper falsiovalis zone because of the presence of Icriodus subterminus YOUNGQUIST, 1947, which first appears within the upper falsiovalis zone (Sandberg &
Dreesen 1984, p. 157; Ziegler & Sandberg 1990, p. 16).
Sample ÇR25 contains the last occurrence of Ancyrodella rotundiloba (BRYANT, 1921), which does not range above the punctata zone (Ziegler & Sandberg 1990, p.
17). Therefore, the stratigraphic interval beginning with Icriodus subterminus and ending with Ancyrodella rotundiloba (Table 1, samples ÇR2-ÇR25) can be correlated with the upper falsiovalis, transitans and punctata zones of Ziegler & Sandberg (1990). Based on the occurrence of Icriodus expansus BRANSON & MEHL, 1938, which ranges into the lower hassi zone, the overlying two samples (ÇR26 and ÇR27) can be assigned to the lower hassi zone (Ziegler & Sandberg 1990, p.
18). Sample ÇR47 (Table 2) includes the lowest occurrence of Polygnathus buddingtoni SAVAGE, 1987, which does not occur below the lower hassi zone (Savage 1987, p. 2324; 1992, p. 278). Therefore, the interval ranging from sample ÇR26 to sample ÇR46 probably comprises the lower hassi, upper hassi and jamieae Zones (Ziegler & Sandberg 1990).
Samples ÇR47 to ÇR90 (Table 2) can be correlated with the lower to upper rhenana Zones of Ziegler &
Sandberg (1990) on the basis of the occurrence of Polygnathus buddingtoni, which was reported from these zones by Savage (1987, p. 2324, 1992, p. 278). Sample ÇR58 is within the lower rhenana zone as it contains the youngest Icriodus subterminus (Ziegler & Sandberg 1984, p. 157, 1990, p. 20). Sample ÇR65 (Table 2) contains the lowest occurrence of Icriodus alternatus
Table 1. Distribution and abundance of Pa elements of conodont taxa. See Figure 2 for sample intervals. ‘?’ indicates questionable identification.
19
2 3 4 5 6 7 9 10 11 12 13 14 15 17 18 20 21 22 23 24 25 26 27 28 29 303233 35
1? 1? 1 1 3
36
2 1 3
3 1 2 3 1
3 8 2 10 5
2 1 9 12 2 45 3 14 3 2 6 1 3 6 3
1 1 3 7 1 2 2 33 5 29 5 10 1 10 1 3 1 5 2 11 4 8
1
1 14 1 2 2 1 1 3 4 3 2 6 1 3 33 1 2 2 42
1 4 12 4 3 2 2 6
15 2 1
6 3 2 1 1 2612726 2 4210011463 1558 2 3 15 2 Ancyrodella binodosa
Ancyrodella rotundiloba
Icriodus excavatus Icriodus expansus Icriodus subterminus Polygnathus aequalis Polygnathus alatus
Po. webbi
Polygnathus aff. xylus SAMPLE (ÇR)
CONODONT ZONE falsiovalis to punctata ? lower to
Polygnathus dubiusaff.
Icriodus brevisaff.
upper hassi jamieae
Table 2. Distribution and abundance of Pa elements of conodont taxa. See Figure 2 for sample intervals. ‘?’ indicates questionable identification.
43 46 47 48 49 50 53 54 58 59 62 63 65 66 67 68 69 77 78 79 82 83 85 86 87 88 89
1 1
1
90 2 37 42
5 5 1 3 8 3 3 10
136 1
1324 5 38
1
1 4 5 1 2 4 8 2 13 54 13 13 9 8 12 39 10 28 31
7
1 3 2
3 2 1 4
2
4 1 12 5 3
27 26 13 1 7 7 66 20 1 4 3 18 13 8 12814 4 2 1 9 8 1
1 4 1 1 3 4 9 3 1 1 7 1 1 1 4 1?1?
2 5 6
1 1
1
6 6 1 1 1 4 8 2 3 1 12 2 5 21 7 11 3 3 2 6 1 6 15 9
SAMPLE (ÇR)
CONODONT ZONE hassi
to jamieae ? lower to upper
Polygnathus aequalis Ancyrodella curvata Ancyrodella lobata Ancyrodella nodosa Icriodus alternatus alternatus Icriodus alternatus helmsi Icriodus excavatus Icriodus iowaensis Icriodus subterminus Icriodus symmetricus
Polygnathus alatus Polygnathus buddingtoni Polygnathus pacificus
Polygnathus webbi
lower rhenana
Icriodus I. symmetricusaff.
Polygnathus Po. procerusaff.
alternatus BRANSON & MEHL, 1934, which first occurs at or just after the start of upper rhenana zone (Ziegler
& Sandberg 1990, p. 21). Therefore the faunas with Icriodus alternatus alternatus within the rhenana zone can be assigned to the upper rhenana zone (Table 2, samples ÇR65-ÇR90).
Although the first occurrence of Palmatolepis triangularis SANNEMANN, 1955a, which defines the base of the triangularis zone, is in sample ÇR135 (Table 4), its base must be below this sample. Another indication of the beginning of the triangularis zone may be the highest range of Polygnathus webbi STAUFFER, 1938, which disappears at the end of the linguiformis zone (the Frasnian-Famennian boundary). Therefore, the range of Polygnathus webbi above the upper rhenana zone (Table 3, sample ÇR91) may represent the linguiformis zone (Ziegler & Sandberg 1990). However, the boundary between the linguiformis zone and the overlying triangularis zone is questionable because of the lack of the diagnostic taxa. Due to the occurrence of Icriodus cornutus, which first appears in the middle of the middle triangularis zone (Ziegler & Sandberg 1990, p. 22), sample ÇR123 can be assigned to the middle triangularis zone.
The first appearence of Palmatolepis crepida, which indicates the base of the crepida zone, is in sample ÇR142 (Table 4). However, a lower sample, ÇR139, contains the first Pelekysgnathus inclinatus THOMAS, 1949 and Polygnathus depressus METZGER, 1989, which have yet to be reported below the crepida zone (Metzger 1989, p.
520; Sandberg & Dreesen 1984, p. 23). Therefore the interval below the lowest occurrence of Palmatolepis crepida SANNEMANN, 1955b, characterized by these two
species, belongs to the crepida zone. Because of the presence of Palmatolepis termini SANNEMANN, 1955b which does not appear before the middle crepida zone, sample ÇR142 is also within the middle crepida zone.
Zonal indices for the rhomboidea zone are not present. Sample ÇR156 is not younger than the marginifera zone because of the last occurrence of Icriodus cornutus, which became extinct within this zone.
A higher sample (Table 4, sample ÇR159) contains the last occurrence of Polygnathus depressus, which ranges from somewhere within the crepida zone to the middle expansa zone (Metzger 1989, p. 520). Therefore, this sample can be assigned to the expansa zone (Ziegler &
Sandberg 1990), if the last occurrence of Polygnathus depressus in sample ÇR159 is not facies-controlled.
Zonal indices for the trachytera, postera and raesulcata Zones are not present. However, based on the presence of Polygnathus zikmundovae ZHURAVLEV, 1991, which first appears at the base of the upper praesulcata zone (Vorontsova 1993, fig. 1), the uppermost two samples (Table 4, samples ÇR168 and ÇR170) of the studied stratigraphic section can be assigned to the upper praesulcata zone (Ziegler &
Sandberg 1984, 1990).
Systematic Palaeontology
A total of 54 conodont species and subspecies has been identified from 107 samples in this study. Herein, only new taxa are discussed. Other generally well known species are illustrated in Plates 1-5, and listed in Tables 1-4. The multi-element notation and familial classification of Sweet (1988) are used in this paper. All studied and/or
10 10 10 10 12 12 12 12 12 12 12 12 13 13 13 13 13 98
97 94 93
91 11
1*
1 1 3 1 2
9 1 9
1* 1* 2*
2 1
1 1 3 4
1?
4 2 61 21 1 2 2
1 1 1
1
1 6 3 9
18
3 4
1 5 2
3 2 2 3 1 3 6 3 1 3 6 8 8
1 4
1 3 1 3 1 5 3 1 5 3 15 70
1 1? 5
1 Icriodus alternatus alternatus
Ancyrodella curvata Ancyrognathus primus
Icriodus alternatus helmsi Icriodus cornutus Icriodus iowaensis
Polygnathus alatus Polygnathus brevilaminus Polygnathus pacificus
Polygnathus webbi
SAMPLE (ÇR)
CONODONT ZONE li.? triangularis
Polygnathus subnormalisaff.
Table 3. Distribution and abundance of Pa elements of conodont taxa. See Figure 2 for sample intervals. ‘?’ indicates questionable identification. * Reworked samples.
illustrated specimens are stored at Karadeniz Teknik Üniversitesi in the Jeoloji Mühendisli¤i Bölümü, Trabzon, Turkey.
Order Ozarkodinida DZIK, 1976 Family Spathognathodontidae HASS, 1959
Genus Mehlina YOUNGQUIST, 1945
Type Species. - Mehlina irregularis YOUNGQUIST, 1945 Mehlina sp. A
Plate 5, Figure 20
Diagnosis: Pa element nearly straight longitudinally, with irregular upper surface denticulation consisting of 14 denticles of unequal size; upper margin profile highest near anterior end, decreasing gradually posteriorward except for slight rising located approximately on middle
part of posterior half; pit at mid-length of the unit, slightly inverted on posterior part: lower margin straight except for slight rising anteriorly of the pit; anterior margin forming an angle of 70 degree with lower margin.
Remarks: The present species is treated in open nomenclature because only a single specimen was found.
Material: 1 Pa element.
Family Palmatolepidae SWEET, 1988 Genus Palmatolepis ULRICH & BASSLER, 1926 Type species. - Palmatolepis perlobata ULRICH &
BASSLER, 1926 Palmatolepis sp. A
Plate 3, Figure 6
135
19 7
12
11
136 137 138 139 141 142 144 147 150 151 153 155 157 158 159 1
1 1
8 2 3 19
13 1 110 110 6 44 20 1? 1?
1 28 31
46 36 7 19 55 2 13 9 21
25 16 2 139 4 56 2
1
2 2 1 1 3
1
1 4 1 2
15 3 3 10 12 1 8 61 4 43 17 3
1 7 3 12
1 1
3 2
3 1
2 2
28 7
1 1
13 1
9 36 3
1
2 5 7 4 4 2
1 10
2 1
6 208 87 70 77 20
9 2
1
13 1 1
1 1 2 2 9
1
156
86+
162 163 164 167 168 170 Ancyrognathus cryptus
Ancyrognathus sinelaminus Bispathodus stabilis Icriodus adanaensis Icriodus alternatus alternatus Icriodus alternatus helmsi Icriodus cornutus Icriodus fekeensis Icriodus iowaensis Icriodus pectinatus Mehlina strigosa Mehlina
Palmatolepis canadensis Palmatolepis crepida
Palmatolepis delicatula delicatula Palmatolepis quadrantinodosalobata Palmatolepis tenuipunctata Palmatolepis termini Palmatolepis triangularis Palmatolepis
Pelekysgnathus inclinatus Pelekysgnathus planus Pelekysgnathus serradentatus Polygnathus antecompressus Polygnathus brevilaminus
Polygnathus communis communis Polygnathus depressus
Polygnathus semicostatus Polygnathus inornatus Polygnathus nodocostatus Polygnathus zikmundovae
Pseudopolygnathus controversus Polygnathus buzmakovi
SAMPLE (ÇR)
CONODONT ZONE triangularis? crepida ? expansa praesulcatato
n.sp.
aff.
sp.A
sp.A
n.sp.
aff.
aff.
aff.
aff.
Table 4. Distribution and abundance of Pa elements of conodont taxa. See Figure 2 for sample intervals. ‘?’ indicates questionable identification.
Diagnosis: Pa element with upper platform surface ornamented with relatively coarse nodes, with incipient lateral lobe; free blade very short; inner platform with strongly convex outline, with bulged anterior part ornamented with coarse nodes; inner platform with coarser and more densely nodular than rest of platform;
incipient outer lobe; outer platform nearly triangular, with slightly concave anterior and posterior margins;
blade-carina slightly sigmoidal; carina consisting of small, low row of nodes posterior of central node; posterior part of platform flexed upward after central node.
Remarks: The present species is treated in open nomenclature because only a single specimen was found.
Material: 1 Pa element.
Family Polygnathidae BASSLER, 1925 Genus Polygnathus HINDE, 1879 Type species.- Polygnathus dubius HINDE, 1879
Polygnathus antecompressus n. sp.
Plate 2, Figures 6-11
Etymology: From Latin, ante, in front and compressus, compression; for its definite lateral constriction on the anterior platform margin.
Holotype: The Pa element illustrated on Plate 2, Figures 9-11.
Type locality: The northeast side of the Göbelli Creek passing through the village of Çürükler, about 9 km northeast of the town of Feke, Adana, Turkey (Figure 1).
Type stratum : Bed of dirty yellow, densely packed, ostracod-brachiopod grainstone, 357.75 m above the base of the studied stratigraphic section; sample ÇR139 (Figure 2).
Material: 86 Pa elements.
Diagnosis: Pa element with platform approximately three-quarters of unit length, constricted in anterior one- third; short carina and adcarinal grooves confined to anterior one-half to one-third of platform; anterior platform margins generally showing rostral development, ornamented by short transverse ridges to nodes or smooth; platform tongue ornamented with many transverse ridges crossing entire platform; free blade
relatively short, comprising about one-fourth of element length.
Description: Platform thick, representing about three-fourths of unit length, with distinct lateral constriction at anterior one-third, with strongly arched lower profile; outer platform margins of dextral and sinistral Pa elements convex; inner margins varying from slightly convex to slightly concave; anterior platform margins with rostral ridge shape in many specimens, smooth or ornamented by short transverse ridges to nodes; platform tongue with transversely planar to slightly convex upper surface, bearing many straight to wavy transverse ridges crossing entire platform;
transverse ridges continuous, interrupted or bifurcated;
in some of the dextral and sinistral Pa elements, right anterior platform margin distinctly higher than left margin; posterior tip of platform pointed to slightly rounded; carina with fused denticles restricted to about anterior one-half to one-third of platform and adcarinal grooves parallel to carina; short free blade about one- fourth of element length, with robust and irregular denticulation; basal cavity small, elliptical, located on about anterior one-fourth of platform where it is curved inward; keel forming sharp-crested ridge, extending to posterior tip of platform.
Remarks: The free blade is broken on all specimens except in the holotype and one paratype. It comprises about one-fourth of the length of the element, and shows a robust and irregular denticulation. One unillustrated specimen, in which the posterior part of the platform and the anterior part of the free blade are missing, has a more regular denticulation with five denticles on the broken free blade.
Pa elements are similar to those of Polygnathus semicostatus BRANSON & MEHL, 1934 in having a platform tongue ornamented with transverse ridges that cross the entire platform, but differ especially in having a distinct lateral constriction on the anterior third of the platform and the anterior platform margins of the rostral ridge shape.
Range: Polygnathus antecompressus n.sp., which was
obtained only from sample ÇR139, belongs to the lower
crepida zone. Evidence for this assignment is its
occurrence below a sample containing Palmatolepis
crepida, Pa. termini, Pa. tenuipunctata, and its association
with Pelekysgnathus inclinatus and Polygnathus depressus, which have yet to be reported below the crepida zone (Metzger 1989, p. 520; Ziegler & Sandberg 1990, p. 23).
Polygnathus zikmundovae ZHURAVLEV, 1991 Plate 5, Figures 23-24
1991 Polygnathus zikmundovae ZHURAVLEV, p. 129-130, Pl. 1, figs. a-d.
Remarks: Polygnathus zikmundovae, which is a member of the "Polygnathus varcus" group of Vorontsova (1993), is characterized by Pa element with a smooth platform with raised margins, a long free blade, and a basal cavity located at the junction of the free blade and the anterior end of the platform.
Material: 13 Pa elements.
Polygnathus aff. xylus STAUFFER, 1940 Plate 1, Figures 1-3
Remarks: The platform, which is generally smooth or ornamented with subdued nodes, has strongly upturned margins with parallel sides. The carina extends beyond the platform margins. The free blade is equal to platform.
The elliptical basal pit is located on the anterior end of the platform. The unit is slightly curved and moderately arched.
According to Kononova & Ovnatanova (personal communication 1996), these Pa elements correspond to the species Polygnathus pseudoxylus of Kononova et al.
(1996).
Material: 608 Pa elements.
Order Prioniodontida DZIK, 1976 Family Icriodontidae MÜLLER & MÜLLER, 1957
Genus Icriodus BRANSON & MEHL, 1938 Type species. - Icriodus expansus BRANSON &
MEHL, 1938
Icriodus adanaensis n. sp.
Plate 4, Figures 23-29
Etymology: From Adana, where these specimens occur.
Holotype: The Pa element illustrated on Plate 4, Figures 23-25.
Type locality: The village of Çürükler, Feke, Adana, Turkey (Figure 1).
Type stratum: Bed of dirty yellow, oxidized, 25-cm- thick, bioclastic packstone, 517.07 m above the base of the studied stratigraphic section; sample ÇR155 (Figure 2).
Material: 32 Pa elements.
Diagnosis: Pa element with a reclined horny cusp of the same height as or slightly higher than other denticles on posterior end of median row; median row denticles alternated by lateral row denticles; element longitudinally straight; platform of maximum width at posterior end of triangular spindle; basal cavity nearly symmetrical, lachrymiform.
Description: Pa element with triangular spindle;
median denticles alternating in alignment with lateral rows; median row of 7-9 denticles, lateral rows of 3-4 denticles; lateral row denticles generally rounded to laterally extended more pronounced posteriorward;
median row denticles rounded to extended longitudinally more prominent posteriorward; posterior extension of median row of two to three denticles; horny cusp strongly reclined, of nearly same height as or slightly higher than other denticles, laterally compressed; unit straight or weakly curved laterally; basal cavity nearly symmetrical, with rounded posterior and pointed anterior end.
Remarks: The Pa elements of Icriodus adanaensis n.sp. have an upper surface denticulation and a cusp development that are closely similar to that of Icriodus cornutus SANNEMANN, 1955b but the former is distinguished by its shorter and wider triangular spindle.
The Pa elements of the latter have a more narrow and
nearly parallel-sided spindle. Furthermore, the middle
row denticles of Icriodus cornutus is more poorly
developed relative to the lateral row denticles.
The Pa elements of Icriodus chojnicensis MATYJA, 1972 possess irregularly developed lateral-row denticles that are neither aligned nor alternating with middle-row denticles.
Range: The specimens were obtained from samples ÇR147, ÇR150, and ÇR155 (Table 4). In sample ÇR147, the presence of Palmatolepis crepida, Pa. tenuipunctata, Pa. termini indicates the crepida zone. However its upper range may extend into the lower rhomboidea zone, because sample ÇR155 marks the highest range of Icriodus iowaensis, which ranges into this zone.
Icriodus fekeensis n. sp.
Plate 4, Figures 16-20
Etymology: From type locality.
Holotype: The Pa element illustrated on Plate 4, Figures 16-18.
Type locality: The village of Çürükler, town of Feke, Adana (Figure 1).
Type stratum: Bed of 8-cm-thick, gray bioclastic pack-/grainstone, 398.25 m above the base of the studied stratigraphic section; sample ÇR142 (Figure 2).
Material: 25 Pa elements.
Diagnosis: Pa element long, narrow, with nearly parallel sides, with semi-alternating, middle- and lateral- row denticles; unit longitudinally straight to slightly curved; cusp slightly to strongly backwardly inclined;
basal cavity asymmetrical, with more prominent spur on posterior inner side in large specimens.
Description: Platform of Pa element narrow, long, with nearly parallel sides; unit longitudinally straight or slightly curved; median- and lateral-row denticles semi- alternated, discrete; lateral row denticles 7-11, with about equal size varying from round to laterally elongate;
median-row denticles 5-8, round to laterally compressed;
posterior extension of median row bearing 2 or 3 denticles; cusp slightly to strongly reclined, not prominently larger than other denticles, laterally compressed in some specimens; upper margin straight to slightly convex, parallel to lower margin in lateral view;
basal cavity varying from nearly symmetrical, drop shaped in small specimens to asymmetrical with prominent sinus on posterior inner side in large specimens.
Remarks: The Pa element of Icriodus fekeensis n. sp.
is similar to that of Icriodus expansus BRANSON & MEHL, 1938 in having an upper-surface denticulation consisting of semi-alternating, median- and lateral-row denticles but differs in having a narrow and extended platform with more or less parallel sides, and in having a basal cavity with a prominent sinus on the posterior inner side. Some Pa elements assigned to Icriodus expansus by Weddige (1984, pl. 4, figs. 67-69) belong probably to Icriodus fekeensis n. sp.
The Pa elements of Icriodus symmetricus differ from Icriodus fekeensis n. sp. in having laterally aligned median- and lateral-row denticles. Furthermore, the former has a characteristic hairline ridge that, in most specimens, connects medial denticles in that part of the platform having three rows of denticles.
Range: Icriodus fekeensis n. sp. has been obtained only from sample ÇR142. Accompanying fauna consist of Palmatolepis crepida, Palmatolepis quadrantinodosalobata, Palmatolepis tenuipunctata, Palmatolepis termini and others belonging to the crepida zone.
Icriodus aff. symmetricus BRANSON & MEHL, 1934 Plate 4, Figures 10-11
Remarks: This species has a nearly straight Pa element with semi-alternating lateral-row and median- row denticles. Posterior extension of median row is of two or three denticles. The laterally compressed median- row denticles are more poorly developed than those of the lateral rows, which are laterally extended and longitudinally discrete.
The Pa elements of Icriodus symmetricus have almost perfectly aligned medial-row and lateral-row denticles.
The most distinguishing feature is the hairline ridge that in most specimens connects medial denticles in that part of the platform having three rows of denticles (Sandberg
& Dreesen 1984).
Material: 12 Pa elements.
Genus Pelekysgnathus THOMAS, 1949 Pelekysgnathus serradentatus ÇAPKINO⁄LU, 1991
Plate 2, Figures 14-15
ABDÜSSELÂMO⁄LU, fi. 1963. Nouvelles observations stratigraphiques et Paléontologiques sur les terrains Paléozoïques affleurant à l’est du Bosphore. Bulletin of the Mineral Research and Exploration Institute of Turkey 60, 1-6.
BASSLER, R.S. 1925. Classification and stratigraphic use of the conodonts. Geological Society of America Bulletin 36, 218-220.
BRANSON, E.B. & MEHL, M.G. 1934. Conodonts from the Grassy Creek Shale of Missouri. The University of Missouri Studies 8, 171-259 [1933].
BRANSON, E.B. & MEHL, M.G. 1938. The conodont genus Icriodus and its stratigraphic distribution. Journal of Paleontology 12, 156-166.
BRYANT, W.L. 1921. The Genesee conodonts with descriptions of new species. Buffalo Society of Natural Sciences Bulletin 13, 1-59.
ÇAPK›NO⁄LU, fi. 1990. Gümüflali Formasyonu’nun (Üst Devoniyen) Çürükler Köyü (Feke, Adana) Yöresindeki Fasiyes Özellikleri ve Conodont Faunas›. Ph.D. thesis, Karadeniz Teknik Universitesi, Trabzon-Türkiye [inTurkish with English abstract].
ÇAPK›NO⁄LU, fi. 1991. A new Pelekysgnathus species from the Lower Famennian of the Taurides, Turkey. Bollettino della Società Paleontologica Italiana 30, 349-353.
ÇAPK›NO⁄LU, fi. 1997. Conodont fauna and biostratigraphy of the Famennian of Büyükada, ‹stanbul, northwestern Turkey.
Bollettino della Società Paleontologica Italiana 35, 165-185 [1996].
DZIK, J. 1976. Remarks on the evolution of Ordovician conodonts. Acta Palaeontologica Polonica 21, 395-455.
GED‹K, ‹. 1975. Die Conodonten der Trias auf der Kocaeli-Halbinsel (Türkei). Palaeontographica Abt. A 150, 99-160.
GED‹K, ‹. 1977. Orta Toroslar’da konodont biyostratigrafisi. Türkiye Jeoloji Kurumu Bülteni 20, 35-48 [in Turkish with English abstract].
HASS, W.H. 1959. Conodonts from the Chappel Limestone of Texas.
U.S. Geological Survey Professional Paper 294-J, 365-399.
References
1991 Pelekysgnathus serradentatus ÇAPKINO⁄LU, p.
351-352, Pl. 1, figs. 1-3.
Remarks: The Pa elements of Pelekysgnathus serradentatus are distinguished by having an irregular upper surface denticulation consisting of short transverse ridges in different lengths that intersect a thin longitudinal ridge, by the lack of a prominent main cusp, and by a broad, subsymmetrical basal cavity.
Material: 13 Pa elements.
Discussions and Conclusions
According to lithologic, faunal and sedimentologic data, the Gümüflali Formation of the eastern Taurides, Turkey was deposited chiefly in a shallow subtidal environment.
Therefore, its conodont fauna generally represents the nearshore polygnathid-"icriodid" biofacies (Sandberg 1976; Sandberg & Dreesen 1984). However, a few conodont species of the palmatolepid-polygnathid biofacies (Sandberg 1976; Sandberg & Dreesen 1984) also occur in some beds. Because of the influence of the biofacies, the samples of the nearshore polygnathid-
"icriodid" and polygnathid-pelekysgnathid biofacies (Sandberg 1976; Sandberg & Dreesen 1984) are difficult to correlate with the standard Late Devonian conodont zonation (Ziegler 1962; Ziegler & Sandberg 1984, 1990), which was developed for the pelagic or offshore
palmatolepid-bispathodid and palmatolepid-polygnathid biofacies (Sandberg 1976; Sandberg & Dreesen 1984).
Also, because of the scarcity of zone fossils and the irregularity of the stratigraphic ranges of present taxa, the direct and accurate correlation of the Gümüflali Formation with the alternate shallow-water conodont zonation (Sandberg & Dreesen 1984) - based on the nearshore facies - is not possible. However, using the stratigraphic ranges of some of the present taxa, an indirect correlation with the standard zonation, was confirmed, and it was determined that the Gümüflali Formation probably belongs to an interval extending from within the Upper falsiovalis zone into the Upper praesulcata zone. These zones were defined from a total of 54 species and subspecies, three of which are new. The approximate zonal boundaries were discussed in the text and presented in Tables 1-4.
Acknowledgements
This study is a contribution to IGCP-421.
The authors are indebted to the personnel of the
General Directorate of Mineral Research and Exploration
(MTA) in Adana for logistical assistance during the
fieldwork, and to Dr. Pierre Bultynck for reading an early
version of the manuscript. Also, we thank Willi Ziegler
and Heinz Kozur for their constructive reviews of the
manuscript. Dr. Steven Mittwede helped with English.
HINDE, G.J. 1879. On conodonts from the Chazy and Cincinnati group of the Cambro-Silurian and from the Hamilton and Genesee shale divisions of the Devonian in Canada and the United States.
Geological Society of London Quarterly Journal 35, 351-369.
KONONOVA, L.I., ALEKSEEV, A.S., BARSKOV, I.S. & REIMERS, A.N. 1996. New species of polygnathid conodonts from the Frasnian of the Moscow syncline. Paleontological Journal translation from Russian Paleontologicheskii Zhurnal 30, 459-465.
KOZUR, H. 1997. The age of the siliciclastic series ("Karareis Formation") of the western Karaburun Peninsula, western Turkey. In: SZANIAVSKI, H. (ed), Proceedings of the Sixth European Conodont Symposium (ECOS VI). Palaeontologica Polonica 58, 171-179.
MATYJA, H. 1972. Biostratigraphy of the Upper Devonian from the borehole Chojnice 2 (western Pomerania). Acta Geologica Polonica 22, 735-750.
MET‹N, S., DEMIRTAflL›, E. & AYHAN, A. 1983. Stratigraphy of the Eastern Taurus autochthon. In: TEKELI O. & GÖNCÜO⁄LU, M.C. (eds), Geology of the Taurus Belt. Proceedings of International Tauride Symposium. Mineral Research and Exploration Institute of Turkey (MTA) Publications, pp. 7-16.
METZGER, R. A. 1989. Upper Devonian (Frasnian-Famennian) conodont biostratigraphy in the subsurface of north-central Iowa and southeastern Nebraska. Journal of Paleontology 63, 503-524.
MÜLLER, K.J. & MÜLLER, E.M. 1957. Early Upper Devonian (Independence) conodonts from Iowa, Part I. Journal of Paleontology 31, 1069-1108.
ÖNDER, F. 1982. New micropalaeontological data and stratigraphical investigations of the Triassic rocks of the Central Taurus Mountains, Turkey. Ph.D. thesis, University of Southampton, England.
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1973. Tufanbeyli dolay›n›n (Do¤u Toroslar, Adana) Kambriyen- Tersiyer Kayalar›. Türkiye Jeoloji Kurumu Bülteni 16, 82-100 [in Turkish with English abstract].
SANDBERG, C.A. 1976. Conodont biofacies of Late Devonian Polygnathus styriacus Zone in western United States. In: BARNES, C.R. (ed), Conodont paleoecology. Geological Association of Canada Special Paper 15, 171-186.
SANDBERG, C.A. & DREESEN, R. 1984. Late Devonian icriodontid biofacies models and alternate shallow-water conodont zonation.
Geological Society of America Special Paper 196, 143-178.
SANNEMANN, D. 1955a. Beitrag zur Untergliederung des Oberdevons nach Conodonten. Neues Jahrbuch für Geologie und Paläontologie Abhandlungen 100, 324-331.
SANNEMANN, D. 1955b. Oberdevonische Conodonten (to II alpha).
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Received 25 February 2000; revised typescript accepted 27 November 2000
PLATE 1
Figures 1-3. Polygnathus aff. xylus STAUFFER, 1940
1. Upper view, ÇR3, x90; 2-3. Upper and lower views, ÇR3, x60.
Figure 4. Polygnathus aff. dubius HINDE, 1879 Upper view, ÇR10, x55.
Figure 5. Polygnathus aequalis KLAPPER and LANE, 1985 Upper view, ÇR35, x60.
Figures 6-8. Polygnathus alatus HUDDLE, 1934
6-7. Upper and lower views, ÇR35, x55; 8. Upper view, ÇR28, x55.
Figures 9-10. Polygnathus brevilaminus BRANSON and MEHL, 1934a 9. Upper view, ÇR137, x62; 10. Lateral view, ÇR137, x62.
Figures 11-14. Polygnathus depressus METZGER, 1989
11-12. Upper and lower views, ÇR147, x62; 13-14. Upper and lower views, ÇR147, x62.
Figure 15. Polygnathus semicostatus BRANSON and MEHL, 1934a Upper view, ÇR142, x45.
Figures 16-19. Polygnathus pacificus SAVAGE and FUNAI, 1980
16-17. Upper and lower views, ÇR90, x60; 18-19. Oblique-lateral and lateral views, ÇR78, x60.
Figure 20. Polygnathus aff. procerus SANNEMANN, 1955b Inner-lateral view, ÇR43, x62.
Figures 21-22. Polygnathus aff. subnormalis VORONTSOVA and KUZMIN, 1984 Upper and lower views, ÇR132, x62.
PLATE 2
Figures 1-2. Polygnathus aff. inornatus BRANSON, 1934 Upper and lower views, ÇR167, x45.
Figure 3. Polygnathus aff. nodocostatus BRANSON and MEHL, 1934a Upper view, ÇR159, x62.
Figures 4-5. Polygnathus aff. buzmakovi KUZMIN, 1990
4. Oblique-upper view, ÇR137, x58; 5. Upper view, ÇR137, x58.
Figures 6-11. Polygnathus antecompressus n. sp.
6. Upper view of paratype, ÇR139, x45; 7. Upper view of paratype, ÇR139, x45; 8. Oblique-lateral view of paratype, ÇR139, x45;
9-11. Upper, oblique-lateral and lower views of holotype, ÇR139, x45.
Figures 12-13. Polygnathus buddingtoni SAVAGE, 1987
12. Upper view, ÇR58, x45; 13. Upper view, ÇR54, x45.
Figures 14-15. Pelekysgnathus serradentatus ÇAPKINO⁄LU, 1991 Upper and lateral views, ÇR137, x40.
Figures 16-17. Polygnathus webbi STAUFFER, 1938 Upper and inner-lateral views, ÇR89, x45.
PLATE 3
Figure 1. Palmatolepis canadensis ORCHARD, 1989 Upper view, ÇR137, x62.
Figure 2. Palmatolepis delicatula delicatula BRANSON and MEHL, 1934a Upper view, ÇR137, x62.
Figure 3. Palmatolepis termini SANNEMANN, 1955b Upper view, ÇR147, x62.
Figure 4. Palmatolepis tenuipunctata SANNEMANN, 1955b Upper view, ÇR142, x62.
Figure 5. Palmatolepis crepida SANNEMANN, 1955b Upper view, ÇR142, x62.
Figure 6. Palmatolepis sp. A Upper view, ÇR137, x66.
Figures 7-8. Palmatolepis triangularis SANNEMANN, 1955a
7. Upper view, ÇR137, x45; 8. Upper view, ÇR135, x62.
Figure 9. Palmatolepis quadrantinodosalobata SANNEMANN, 1955a Upper view, ÇR141, x62.
Figure 10. Ancyrognathus sinelamina (BRANSON and MEHL, 1934a) Upper view, ÇR137, x45.
Figure 11. Ancyrodella nodosa ULRICH and BASSLER, 1926 Upper view, ÇR79, x60.
Figure 12. Ancyrognathus primus JI, 1986 Upper view, ÇR132, x60.
Figures 13-14. Ancyrognathus cryptus ZIEGLER, 1962 Upper and lower views, ÇR137, x60.
Figure 15. Ancyrodella lobata BRANSON and MEHL, 1934a Upper view, ÇR59, x60.
Figure 16. Ancyrodella curvata (BRANSON and MEHL, 1934a) Upper view, ÇR90, x60
PLATE 4
Figures 1-4. Icriodus expansus BRANSON and MEHL, 1938
1-2. Upper and lower views, ÇR10, x62; 3-4. Upper and lower views, ÇR10, x62.
Figure 5. Icriodus alternatus alternatus BRANSON and MEHL, 1934a Upper view, ÇR137, x62.
Figures 6-7. Icriodus alternatus helmsi SANDBERG and DREESEN, 1984 6. Upper view, ÇR137, x62; 7. Upper view, ÇR137, x62.
Figures 8-9. Icriodus subterminus YOUNGQUIST, 1947
8. Lateral view, ÇR46, x62; 9. Lateral view, ÇR14, x62.
Figures 10-11. Icriodus aff. symmetricus BRANSON and MEHL, 1934a Upper and lower views, ÇR48, x62.
Figures 12-15. Icriodus cornutus SANNEMANN, 1955b
12-13. Upper and inner-lateral views, ÇR132, x62; 14-15. Upper and lateral views, ÇR138, x62.
Figures 16-20. Icriodus fekeensis n. sp.
16-18. Upper, outer-lateral and lower views of holotype, ÇR142, x62; 19-20. Upper and lower views of paratype, ÇR142, x62.
Figures 21-22. Icriodus symmetricus BRANSON and MEHL, 1934a 21. Upper view, ÇR46, x62; 22. Upper view, ÇR46, x62.
Figures 23-29. Icriodus adanaensis n. sp.
23-25. Upper, lateral and lower views of holotype, ÇR147, x60; 26-27. Upper and lateral views of paratype, ÇR155, x60; 28-29.
Upper and lateral views of paratype, ÇR155, x60.
PLATE 5 PLATE 5
Figures 1-2. Bispathodus stabilis (BRANSON and MEHL, 1934a) Lateral and lower views, ÇR170, x60.
Figure 3. Pseudopolygnathus aff. controversus SANDBERG and ZIEGLER, 1979 Upper view, ÇR163, x60.
Figure 4. Pelekysgnathus inclinatus THOMAS, 1949 Lateral view, ÇR142, x55.
Figures 5-6. Ancyrodella binodosa UYENO, 1967 Upper and inner lateral views, ÇR25, x60.
Figure 7. Ancyrodella rotundiloba (BRYANT, 1921) Upper view, ÇR25, x60.
Figures 8-12. Icriodus excavatus WEDDIGE, 1984
8. Upper view, ÇR77, x55; 9. Upper view, ÇR78, x55; 10-12. Upper, outer-lateral, and lower views, ÇR77, x62.
Figures 13-14. Icriodus aff. brevis STAUFFER, 1938 Upper and lateral views, ÇR77, x62.
Figures 15-16. Icriodus aff. pectinatus DREESEN and HOULLEBERGHS, 1980 Upper and lateral views, ÇR147, x62.
Figures 17-19. Icriodus iowaensis YOUNGQUIST and PETERSON, 1947
17-18. Upper and lateral views, ÇR131, x62; 19. Upper view, ÇR133, x62.
Figure 20. Mehlina sp. A
Lateral view, ÇR159, x45.
Figure 21. Mehlina strigosa (BRANSON and MEHL, 1934a) Lateral view, ÇR156, X45.
Figure 22. Pelekysgnathus planus SANNEMANN, 1955b Lateral view, ÇR137, x55.
Figures 23-24. Polygnathus zikmundovae ZHURAVLEV, 1991 Upper and lower views, ÇR170, x60.
Figures 25-26. Polygnathus communis communis BRANSON and MEHL, 1934b Upper and lower views, ÇR167, x50.
